Distributed Deformation Across the Rio Grande Rift, Great Plains, and Colorado Plateau

Geology, 40(1), 23-26, 2012 Distributed Deformation across the Rio Grande Rift, Great Plains, and Colorado Plateau Henry T. Berglund1, Anne F. Sheehan2, Mark H. Murray3, Mousumi Roy4, Anthony R. Lowry5, R. Steven Nerem6, and Frederick Blume1 1UNAVCO Inc, 6350 Nautilus Drive, Boulder, Colorado 80301-5553, USA 2Department of Geological Sciences, University of Colorado, Boulder, Colorado 80309-0399, USA 3Department of Earth and Environmental Science, New Mexico Tech, Socorro, New Mexico 87801, USA 4Department of Earth & Planetary Sciences, University of New Mexico, Albuquerque, New Mexico 87131-1116, USA 5Department of Geology, Utah State University, Logan, Utah 84322-4505, USA 6Department of Aerospace Engineering Sciences, University of Colorado, Boulder, Colorado 80309-0429, USA ABSTRACT We use continuous measurements of GPS sites from across the Rio Grande Rift, Great Plains, and Colorado Plateau to estimate present-day surface velocities and strain rates. Velocity gradients from five east-west profiles suggest an average of ~1.2 nanostrains/yr east-west extensional strain rate across these three physiographic provinces. The extensional deformation is not concentrated in a narrow zone centered on the Rio Grande Rift but rather is distributed broadly from the western edge of the Colorado Plateau well into the western Great Plains. This unexpected pattern of broadly distributed deformation at the surface has important implications for our understanding of how low strain-rate deformation within continental interiors is accommodated. INTRODUCTION Global positioning system (GPS) monuments installed for the EarthScope Plate Boundary Observatory (PBO) and the Rio Grande Rift GPS experiment (Fig. 1) have greatly enhanced modern geodetic coverage of the physiographic regions of the Rio Grande Rift and the Colorado Plateau. More than 4 yr of continuous measurement at these sites provide a detailed map of the contemporary motion across the southwestern United States, where prior geodetic measurements are sparse and highly uncertain. Argus and Gordon (1996), using very long baseline interferometry (VLBI), found that the velocity of two sites on the Colorado Plateau differed from stable North America with upper bounds of ~4–5 mm/yr. At shorter spatial scales, classical trilateration across the Rio Grande Rift near Socorro, New Mexico, found no significant extension across the rift and gave an upper bound of ~1 mm/yr (Savage et al., 1980). Estimates of extension using geological methods in the Albuquerque Basin are on the order of 0.3 mm/yr (Woodward, 1977), while Golombek et al. (1983) estimated a rate of ~0.14 mm/yr across the Espanola basin in northern New Mexico for 5 Ma to present. More recently Kreemer et al. (2010) used PBO measurements to show that the western portion of the Colorado Plateau is moving westward ~1 mm/yr relative to stable North America. They did not detect significant extension across most of the Rio Grande Rift, except a possible ~0.5 mm/yr in the southernmost region. Here we estimate horizontal velocities for 284 continuously measured GPS monuments in a region straddling the Rio Grande rift and bordered by the southern Basin and Range to the south, the Great Plains to the east, and the northern Basin and Range to the west. Using these velocities, we investigate the contemporary kinematic field and calculate deformation rates along east-west velocity profiles across the study area (Fig. 1). Geology, 40(1), 23-26, 2012 Figure 1. Global positioning system (GPS) monuments in vicinity of the Rio Grande Rift and southern Rocky Mountains. The Rio Grande Rift Earthscope GPS experiment included construction of 25 GPS monuments (blue circles) in Colorado and New Mexico in 2006 and 2007. Regional EarthScope Plate Boundary Observatory and Continuously Operating Reference Station monuments are shown by gray triangles. Black lines denote major physiographic boundaries (Fenneman and Johnson, 1946). Basins referred to in text: SL—San Luis, E—Espanola, A— Albuquerque, JM—Jornado del Muerto, T—Tularosa. Red traces show location of the Wasatch fault zone in north-central Utah and the Williams Fork Mountains fault in north-central Colorado (U.S. Geological Survey and Colorado Geological Survey, 2006). ––––––––––––––––––––– TECTONIC SETTING The surface expression of the Rio Grande Rift consists of a series of interconnected, north- south–trending asymmetrical grabens. Clearly defined rift grabens extend from Leadville, Colorado, in the north to Socorro, New Mexico, in the south, and include the San Luis, Espanola, and Albuquerque Basins. The rift’s fault-bounded basins are narrower in Colorado and northern New Mexico and widen southward, with widths ranging from ~25 to 50 km (Cordell, 1978). In addition, the rift geometry changes southward from a linear chain of narrow grabens to multiple, Geology, 40(1), 23-26, 2012 adjacent basins (e.g., the Jornada del Muerto and Tularosa Basins) as the rift transitions into the southern Basin and Range province between profiles 4 and 5 (Fig. 2). At depth, the seismic data show anomalously slow upper-mantle seismic velocity in a broad zone around the rift, continuing beyond the geologically mapped boundaries well into the Colorado Plateau and extending north into the southern Rocky Mountains (Lee and Grand, 1996; Dueker et al., 2001; Gao et al., 2004; Burdick et al., 2009). Upper mantle seismic attenuation (Q) maps show narrow zones of low Q correlated with the zone of surficial grabens rather than the region of low seismic velocities (Boyd and Sheehan, 2005). If low effective viscosity in the upper mantle correlates with the seismic velocity picture, then kinematic extension in the Rio Grande Rift may actually be broader than the surficial geologic boundaries of the rift. In contrast, if low effective viscosity in the upper mantle correlates with the attenuation anomaly, then extension is likely to localize in a narrow region correlating with surficial grabens. Contemporary crustal stress in western Colorado includes a roughly northeast-oriented extensional axis based on inversion of earthquake focal mechanisms (Bott and Wong, 1995). Seismicity within the Rio Grande Rift is dominantly normal faulting, with a minor amount of strike-slip (Keller et al., 1991; Herrmann et al., 2011). A disproportionate fraction of earthquake activity in New Mexico occurs in the middle of the Rio Grande Rift at Socorro, related to the Socorro magma body (e.g., Balch et al., 1997). GPS RESULTS AND INTERPRETATION We use data from 25 continuous GPS stations installed as part of the EarthScope Rio Grande Rift GPS experiment, supplemented by data from other GPS monuments in the southwestern United States, resulting in a data set of daily position estimates of 284 GPS monuments for the years 2006 through 2010. We use the GAMIT/GLOBK software (King and Bock, 1999) to obtain daily coordinates for the stations in the Rio Grande Rift GPS Experiment and for an additional 29 sites that are part of the Continuously Operating Reference Station (CORS) network (Snay and Soler, 2008; http://www.ngs.noaa.gov/CORS/). We combine the aforementioned position estimates with GPS coordinate estimates for 230 continuous sites available in the Solution Independent Exchange format (SINEX) from the PBO (http://pbo.unavco.org/data/gps). We constrain the rotation of North America by estimating six Helmert parameters (three translation, three rotation) for each day so that adjustments to a predetermined set of a priori values for a chosen group of stations are minimized. The a priori values for the stations that we use to constrain the rotation of North America are tabulated in Table DR1 in the GSA Data Repository1. We exclude sites located outside 28°N–65°N and 116°W–60°W from our analysis. We estimate velocities and uncertainties from the resulting position time series using the GAMIT/GLOBK software and account for annual and semi-annual sinusoidal terms in each time series. We restrict our analysis by excluding sites with <2.5 yr of data. The velocity estimates are tabulated in Table DR2 and shown in Figure 2. Horizontal velocities, shown in Figure 2, increase in magnitude from east to west toward the Pacific–North America plate margin in California. Velocity estimates in Idaho, northern Utah, northern Nevada, Wyoming, and Montana show a smooth clockwise rotation. This rotational pattern is consistent with prior results showing large-scale rotation about an axis in eastern Oregon (e.g., McCaffrey et al. 2007). Sites east of the Rio Grande Rift in eastern Colorado, eastern New Mexico, Texas, Oklahoma, Kansas, and Nebraska move very slowly (~<1mm yr–1) with respect to the North America frame. Geology, 40(1), 23-26, 2012 Figure 2. Locations of profile lines as numbered; west end of each profile line is the left side of Figure 3. Arrows indicate the direction and magnitude of GPS velocity estimates. Ellipses are 95% confidence. Thick black lines denote major physiographic boundaries (Fenneman and Johnson, 1946): MRM—middle Rocky Mountains, WB—Wyoming Basin, SRM—southern Rocky Mountains, CP—Colorado Plateau, GP—Great Plains, BR—Basin and Range. Light gray lines indicate state boundaries. Latitude at which each profile passes through 109°W is labeled on the right. Gray shaded region in Colorado and New Mexico indicates the rough extent of Rio Grande Rift basins. Williams Fork Mountains fault in north-central Colorado is indicated with a thick gray trace. ––––––––––––––––––––– To estimate strain rates, we project the observed GPS velocities onto five profiles (Fig. 2). The five profiles are oriented approximately parallel to the azimuths of the GPS velocities (N87E) along great circles that pass through 109°W at the labeled latitude (Fig. 2). The velocity components parallel to each profile are related to their distance along the profile (Fig. 3). Profiles include sites within ±100 km normal to each line (Fig. 2). We exclude sites with horizontal uncertainties >0.5 mm/yr from this analysis. Using weighted least squares linear regressions of Geology, 40(1), 23-26, 2012 the velocities, we calculate strain rates for several different distance intervals along profile lines 1–5.

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